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Tuck, A. Molecular to Meteorological. Encyclopedia. Available online: https://encyclopedia.pub/entry/21477 (accessed on 07 October 2024).

Tuck A. Molecular to Meteorological. Encyclopedia. Available at: https://encyclopedia.pub/entry/21477. Accessed October 07, 2024.

Tuck, Adrian. "Molecular to Meteorological" *Encyclopedia*, https://encyclopedia.pub/entry/21477 (accessed October 07, 2024).

Tuck, A. (2022, April 07). Molecular to Meteorological. In *Encyclopedia*. https://encyclopedia.pub/entry/21477

Tuck, Adrian. "Molecular to Meteorological." *Encyclopedia*. Web. 07 April, 2022.

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The path from molecular to meteorological scales begins with the persistence of molecular velocity after collision inducing symmetry breaking, from continuous translational to scale invariant, associated with the emergence of hydrodynamic behaviour in a Maxwellian (randomised) population undergoing an anisotropic flux. The statistical multifractal formulation of observed atmospheric variability enables the examination of turbulence. The unexpected correlation between the intermittency of temperature and the ozone photodissociation rate in the lower Arctic stratosphere led to an analysis of the role of Gibbs free energy in the general circulation of the atmosphere, and a suggestion to solve the persistent cold bias in its siumlation by free running numerical models.

molecular velocity
hydrodynamic emergence
statistical multifractality
Gibbs free energy

The coupling of molecular and meteorological processes is shown schematically in **Figure 1**. It is through the central variable of temperature.

The persistence of molecular velocity after collision ^{[1]} breaks the continuous translational symmetry (randomness) assumed in speed and direction that underlies the Maxwell–Boltzmann probability distribution function (PDF) and hence Lorentzian and Doppler spectral line shapes used in radiative transfer in the atmosphere. Einstein–Smoluchowski diffusion is also negated in the atmosphere and with it the definition of temperature used in laboratories. Maxwell–Boltzmann PDFs have continuous translational symmetry, which is broken by the persistence of velocity after collision.

(1)

The persistence ratio ϖ_{12} is the ratio of the mean velocity after collision to that before collision between molecules of masses *m*_{1} and *m*_{2}. If *m*_{1} = *m*_{2} then ϖ_{12} = 0.406, but in general for *m*_{1} ≠ *m*_{2} the heavier molecule will be slowed less than the lighter one.

This breaking of continuous translational symmetry will be discussed further later in the light of observational analyses, but it immediately leads to the interpretation of molecular dynamics calculations that showed the emergence of hydrodynamic behaviour in a population of randomised molecules subject to an anisotropic molecular flux ^{[2]}. This phenomenon is shown in **Figure 2**. Here ‘molecules’ are represented as hard spheres (‘billiard balls’); ring currents—vortices—emerged on very short time and space scales.

It is suggested from the outset that a vorticity approach be adopted from this smallest, molecular scale. Let **ω** be the vorticity of the field of molecular velocity **v** ^{[3]}:

(2)

This enables calculation of twice the enstrophy directly by taking the curl of the molecular velocity field

(3)

Because enstrophy propagates downscale, in 2D theory at least, it may be less suited to describing the behaviour of energy deposited on the smallest scales, that of photons and molecules as it is in the atmosphere. The vorticity correlation function can lead to the vorticity form of the Navier–Stokes equation; see Section 3.3 of ^{[4]}. Nevertheless, the vorticity of ‘air’ in a molecular dynamical calculation is obtainable by:

(4)

where *p* is molecular momentum and *q* is molecular position. They are necessitated by the non-spherical symmetries of real molecules and the omnipresent anisotropies of gravity, planetary rotation and the solar beam. The nth moment of the molecular speed is ^{[3]}^{[4]}^{[5]}:

(5)

This equation permits *n* to be used in calculating moments in the course of statistical multifractal analysis of molecular dynamics calculations.

Extant statistical multifractal analyses expected temperature to scale like a passive scalar (a tracer), but the earliest such treatments of NASA ER-2 data in the lower stratosphere at 17–20 km altitude showed that temperature scaled differently than known tracers ^{[6]}^{[7]}^{[8]}, at least under rescaled range analysis. With the availability of high-resolution GPS dropsonde data from the NOAA Gulfstream G4-SP, it became clear from statistical multifractal analyses that temperature was affected differently by gravity than other variables ^{[4]}^{[9]}^{[10]}^{[11]}. The scaling of temperature spans the range from micro (molecular) through meso (nanometres to micrometres) to macro (>micrometres). That accounts for temperature acting as a kind of integrator in the way that other variables do not.

A further implication of the Alder–Wainwright mechanism is in the basis of the fluctuation–dissipation theorem as embodied in the Langevin equation. Langevin treated the mean as organised behaviour and fluctuations as dissipation. The Alder–Wainwright mechanism implies the reverse, that the hydrodynamic fluctuation carried by the fastest molecules represents emergent organisation and the mean represented by the near average molecules represents dissipation that defines an effective temperature.

It cannot expect to view atmospheric vorticity in two dimensions and remain quantitative, because the dimensionality of atmospheric flow is 2 + *H*(s), ^{[12]}^{[13]}^{[4]} where *H*(s) is the vertical scaling exponent of the horizontal wind, s. The vorticity form of the Navier–Stokes equation is:

(6)

where κ is kinematic viscosity. The first term on the right says that vorticity,* ***ω**, advects itself: nonlinearity is inherent. This term alone is responsible for much of the complexity and difficulty associated with understanding, describing and computing atmospheric flow. **ω** is defined by Equations (2) and (3) and using (3) it can relate the autocorrelation function for vorticity, A(*t*), to the enstrophy *ε*:

(7)

Enstrophy is governed by:

(8)

where *Str*_{ij} is the straining rate on a fluid element.

Equation (8) expresses the generation of vorticity by stretching, or its destruction by compression, via the first term, balanced by viscous dissipation in the second term. The third term is the divergence, often assumed to be locally zero; this cannot be strictly true, for example, if ozone photodissociation is leading to the generation of vorticity. Considering the theoretical case of 2D turbulence, there are reverse cascades of energy and enstrophy, upscale for the former and downscale for the latter. If photon energy is directly converted to vorticity as implied by the Alder–Wainwright mechanism, it would imply energy transfer upscale from the smallest, molecular, ones in the range of 10–100 nanometres at tropospheric temperatures and pressures. However, the point is moot because the scale invariant structure of the fluctuating abundances of the absorbers and emitters of radiation, including ozone, carbon dioxide, methane, nitrous oxide, halocarbons, aerosols and water in all its phases, means that energy is input and lost to air on all scales, eliminating the possibility of conservative energy or enstrophy cascades either upscale or downscale. The observed scale invariant 23/9 dimensionality of air also eliminates 2D theories from relevance.

The variability in air is defined by three multifractal scaling exponents, which have been evaluated from observations of adequate quality ^{[14]}^{[15]}^{[16]}^{[17]}. The mathematical structure underlying the definition of *H*, *C*_{1} and *α* may be found in these references; the notation is that in ^{[15]}^{[16]}. **Table 1** shows equivalences between the variables of equilibrium statistical thermodynamics and the scaling variables from statistical multifractal analysis as applied to open, non-equilibrium systems, which the atmosphere is. The equivalences in **Table 1** result from mappings ^{[14]} via Legendre transforms; they are not merely formal similarities and lead to the thermodynamic form of multifractality ^{[16]}.

Variable | Statistical Thermodynamics | Scaling Equivalent |
---|---|---|

Temperature | T |
1/qk_{Boltzmann} |

Partition function | f |
e^{−K(q)} |

Energy | E |
γ |

Entropy | −S(E) |
c(γ) |

Gibbs free energy | −G |
K(q)/q |

The variables are obtained as follows. *q* defines the qth order structure function of the observed quantity. The scaling exponent K(*q*) is derived from the slope of a log–log plot of the signal fluctuations versus its range, and *H* is obtained from:

(9)

and examination of energy *E* in terms of a scale ratio produces an expression for the fractal co-dimension *c*(*γ*). *C*_{1} is the co-dimension of the mean, characterising the intensity of the intermittency. The Lévy exponent α characterises the generator of the intermittency which is the logarithm of the turbulent flux; for a real system, its value may not be confined to the theoretical range.

In practice here it find *H* = 0.56, *C*_{1} = 0.05 and *α* = 1.60. The theoretical ranges are 0 < *H* < 1; 0 < *C*_{1} < 1 and 0 < *α* < 2. A Gaussian has *H* = 0.50, *C*_{1} = 0 and *α* = 2. See ^{[4]}^{[15]}^{[16]} for further discussion, and below for analysis of observations. The actual values of the three scaling exponents for wind, temperature, ozone and other molecules may provide information about the variables and how they interact.

If the vertical scaling of temperature is calculated via spectral analysis, assuming for the purpose that intermittency is negligible, the value of H is approximately 5/4 while H for wind speed and relative humidity remains unchanged from the values in **Figure 4**b,c, respectively. The different scaling for temperature has been attributed to the effect of gravity on air density, upon which it acts directly, unlike wind speed and relative humidity ^{[18]}. It will be seen later that the effects of scaling in jet streams are also significant.

The dropsonde results are also apparent in stability analyses of all drops treated fractally ^{[10]}. The results were valid for dry adiabatic, dynamic (Richardson number) and moist adiabatic approaches. The correlation co-dimensions were respectively 0.36, 0.22 and 0.15, a demonstration of the importance of wind shear and moisture compared to a static dry adiabatic analysis. The corresponding fractal dimensions of the Cantoresque set are 0.64, 0.78 and 0.85.

In **Figure 5**, for one descent at 500 and 50 m resolutions, a broadly unstable lower troposphere and stable upper troposphere is seen, whereas at 15 m there are embedded unstable layers within stable layers at all scales, forming a ‘Russian doll’ structure characterised by a fractal dimension of 0.65. There are no unstable layers below about 50 m vertical dimension. This sonde was one of a pair dropped simultaneously; the high correlation of the structures seen by the two sondes eliminates the possibility that the signal is generated by noise ^{[10]}.

Composite variograms from all 246 useable dropsondes during the Winter Storms 2004 mission, involving 10 flights over a wide area of the eastern Pacific Ocean of the Northern Hemisphere ^{[11]}, are shown in **Figure 6**. See ^{[4]}^{[10]}^{[11]} for further description and analysis.

The ‘horizontal’ scaling of the aircraft observations has been calculated separately for the NASA ER-2 and WB57F mainly in the lower stratosphere, and for the NOAA G4-SP and NASA DC-8 mainly in the upper troposphere ^{[4]}. It note that there is an element of vertical velocity in such flight segments ^{[19]}, and that during their ‘vertical’ segments the results for temperature, wind speed and humidity for the scaling exponent H agreed within 10% with the dropsonde results in the previous section ^{[4]}^{[11]}. The missions concerned ranged from pole to pole ^{[4]}^{[11]}^{[20]} when the DC-8 is included.

The intimate connection between molecular behaviour and temperature seen earlier necessitates further examination of the behaviour of temperature in terms of its PDF, intermittency and the correlation of the latter with the ozone photodissociation rate. The observations were taken in the lower stratosphere during Arctic summer (April–September) in 1997 (POLARIS) and Arctic winter (January–March) in 2000 (SOLVE). **Figure 9** shows the highly non-Gaussian PDFs. These missions had measurements of the ozone photodissociation rate ^{[23]} and are discussed in ^{[3]}^{[4]} and in the next section.

The relation between temperature and molecular velocity is given by equations 3.1 and 5.1 of ^{[4]}:

An unexpected result from the measurement ^{[23]} of the ozone photodissociation rate, *J*[O_{3}], was positive correlation with the intermittency of temperature, *C*_{1}(T). That triggered a search for an explanation, with the causal attribution being the production of translationally hot O and O_{2} photofragments recoiling into and acting in the vortices produced by the mechanisms seen in **Figure 1** and justified in references ^{[3]}^{[4]}^{[24]}. The results from POLARIS in the Arctic summer of 1997 and from SOLVE in the Arctic winter of 2000 are displayed in **Figure 10**. *C*_{1} (*T*) is positively correlated both with the ozone photodissociation rate and with temperature itself. By viewing **Figure 9** in conjunction with **Figure 10** and **Figure 11**, it can conclude that atmospheric temperature is not that of a gas in local thermodynamic equilibrium ^{[18]}^{[25]}. Account must be taken of molecular behaviour from the smallest scales up to the gravest; it will mean acting on the persistence of molecular velocity after collision ^{[1]} and its breaking of continuous translational symmetry of a thermalised gas via the Alder–Wainwright mechanism ^{[2]}.

Given that the airborne in situ measurements of molecular species and photodissociation rates are unlikely to become routine, and are presently unattainable from satellite remote sounding, what can be done? Either locally by airborne methods or globally by satellites, it is not foreseeable to the extent necessary. One alternative approach is outlined in ^{[16]}, where the thermodynamic form of statistical multifractality ^{[14]} is adapted ^{[16]} to produce **Table 1**. Those results enable diagnosis of steady states and system directionality from winds and temperatures, which are observed globally in a routine manner. The results in ^{[16]} vindicate the ‘bare’ cascade models of Schertzer and Lovejoy ^{[13]} and Lovejoy and Schertzer ^{[14]} by producing results from ‘dressed’ curves such as that in **Figure 12**, based on the data in **Figure 11**. Similar results were obtained for wind speed and ozone and are representative of all suitable 140 ER-2 flight segments between 1987 and 2000. Here, it is suggested that these diagnostics should prove applicable to global atmospheric models, particularly those dealing with air pollution and climate, wherein molecular species have to be simulated. Gibbs free energy does the work that drives the circulation to a different steady state under a perturbation, either on cooling or heating, after the entropic effects of dissipation have been accounted for.

What molecular behaviour should be expected in the nonequilibrium conditions displayed in **Figure 11** and **Figure 12**? How will translationally hot and rotationally hot air molecules be manifest, whether observed by, for example, direct molecular beam sampling instruments or calculated by molecular dynamics methods? The red curve in **Figure 13** is a hypothetical curve of the PDF of such molecular velocities, whereas the black curve represents an equilibrium Maxwell–Boltzmann state. The difference of the integrals beneath them via Equation (10) provides the Gibbs free energy. The atomic and molecular fragments from ozone photodissociation, which happens from the ultraviolet Hartley band through the Huggins, Chappuis and Wulf bands that stretch across the visible to the near infrared, can have up to an order of magnitude more energy than the average molecules.

- Chapman, S.; Cowling, T.G. The Mathematical Theory of Non-Uniform Gases, 3rd ed.; Chapter 5.5; Cambridge University Press: Cambridge, UK, 1970; pp. 96–99.
- Alder, B.J.; Wainwright, T.E. Decay of the velocity autocorrelation function. Phys. Rev. A 1970, 1, 18–21.
- Tuck, A.F.; Hovde, S.J.; Richard, E.C.; Gao, R.-S.; Bui, T.P.; Swartz, W.H.; Lloyd, S.A. Molecular velocity distributions and generalized scale invariance in the turbulent atmosphere. Faraday Discuss. 2005, 130, 181–193.
- Tuck, A.F. Atmospheric Turbulence: A Molecular Dynamics Perspective; Oxford University Press: Oxford, UK, 2008.
- Landau, L.D.; Lifshitz, E.M. Course of Theoretical Physics, Volume 5, Statistical Physics, 3rd ed.; Part 1, §29; Butterworth-Heinemann: Oxford, UK, 1980.
- Tuck, A.F.; Hovde, S. An examination of stratospheric aircraft data for small-scale variability and fractal character. In Mesoscale Processes in the Stratosphere: Air Pollution Report 69; European Commission: Luxembourg, 1999; pp. 249–254.
- Tuck, A.F.; Hovde, S.J. Fractal behavior of ozone, wind and temperature in the lower stratosphere. Geophys. Res. Lett. 1999, 26, 1271–1274.
- Tuck, A.F.; Hovde, S.J.; Richard, E.C.; Fahey, D.W.; Gao, R.-S. A scaling analysis of ER-2 data in the inner vortex during January-March 2000. J. Geophys. Res. D 2003, 108, 8306.
- Lovejoy, S.; Tuck, A.F.; Hovde, S.J.; Schertzer, D. Is isotropic turbulence relevant in the atmosphere? Geophys. Res. Lett. 2007, 34, L15802.
- Lovejoy, S.; Tuck, A.F.; Hovde, S.J.; Schertzer, D. Do stable atmospheric layers exist? Geophys. Res. Lett. 2008, 35, L01802.
- Hovde, S.J.; Tuck, A.F.; Lovejoy, S.; Schertzer, D. Vertical scaling of temperature, wind and humidity fluctuations: Dropsondes from 13 km to the surface of the Pacific Ocean. Int. J. Remote Sens. 2011, 32, 5891–5918.
- Schertzer, D.; Lovejoy, S. Physical modeling and analysis of rain and clouds by anisotropic scaling multiplicative processes. J. Geophys. Res. D 1987, 92, 9693–9714.
- Schertzer, D.; Lovejoy, S. (Eds.) Non-Linear Variability in Geophysics: Scaling and Fractals; Kluwer Academic Publishers: Dordrecht, The Netherlands, 1991.
- Lovejoy, S.; Schertzer, D. The Weather and Climate: Emergent Laws and Multifractal Cascades; Cambridge University Press: Cambridge, UK, 2013.
- Tuck, A.F. From molecules to meteorology via turbulent scale invariance. Q. J. R. Meteorol. Soc. 2010, 136, 1125–1144, Erratum in Q. J. R. Meteorol. Soc. 2011, 137, 275.
- Tuck, A.F. Proposed empirical entropy and Gibbs energy based on observations of scale invariance in open nonequilibrium systems. J. Phys. Chem. A 2017, 121, 6620–6629.
- Lovejoy, S. Weather, Macroweather and the Climate; Oxford University Press: Oxford, UK, 2019.
- Tuck, A.F. Turbulence: Vertical shear of the horizontal wind, jet streams, symmetry breaking, scale invariance and Gibbs free energy. Atmosphere 2021, 12, 1414.
- Lovejoy, S.; Tuck, A.F.; Schertzer, D.; Hovde, S.J. Reinterpreting aircraft measurements in anisotropic scaling turbulence. Atmos. Chem. Phys. 2009, 9, 5007–5025.
- Tuck, A.F.; Baumgardner, D.; Chan, K.R.; Dye, J.E.; Elkins, J.W.; Hovde, S.J.; Kelly, K.K.; Loewenstein, M.; Margitan, J.J.; May, R.D.; et al. The Brewer-Dobson circulation in the light of high altitude in situ aircraft observations. Q. J. R. Meteorol. Soc. 1997, 123, 1–69.
- Tuck, A.F.; Hovde, S.J.; Kelly, K.K.; Mahoney, M.J.; Proffitt, M.H.; Richard, E.C.; Thompson, T.L. Exchange between the upper tropical troposphere and the lower stratosphere studied with aircraft observations. J. Geophys. Res. 2003, 108, 4734.
- Tuck, A.F.; Hovde, S.J.; Bui, T.P. Scale invariance in jet streams: ER-2 data around the lower-stratospheric polar night vortex. Q. J. R. Meteorol. Soc. 2004, 130, 2423–2444.
- McElroy, C.T. A spectroradiometer for the measurement of direct and scattered solar irradiance from on-board the NASA high altitude research aircraft. Geophys. Res. Lett. 1995, 22, 1361–1364.
- Tuck, A.F. Scale invariant turbulence and Gibbs free energy in the atmosphere. In Entropy and Exergy in Renewable Energy; Wang, L.-S., Ed.; Chapter 5; IntechOpen: London, UK, 2021.
- Tuck, A.F. Theoretical chemistry and the calculation of the atmospheric state. Atmosphere 2021, 12, 727.

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